Geofluids
Volume 2019 (2019), Article ID 3240697, 12 pages
https://doi.org/10.1155/2019/3240697

Research Article

The Distribution of Dissolved Methane and Its Air-Sea Flux in the Plume of a Seep Field, Lingtou Promontory, South China Sea

Pengfei Di,¹ Dong Feng,1,2,3 and Duofu Chen2,3

¹CAS Key Laboratory of Ocean and Marginal Sea Geology, South China Sea Institute of Oceanology, Chinese Academy of Sciences, Guangzhou, Guangdong 510301, China
²Laboratory for Marine Mineral Resources, Qingdao National Laboratory for Marine Science and Technology, Qingdao 266061, China
³Shanghai Engineering Research Center of Hadal Science and Technology, College of Marine Sciences, Shanghai Ocean University, Shanghai 201306, China

Correspondence should be addressed to Pengfei Di; pfd@scsio.ac.cn

Received 24 January 2019; Accepted 18 June 2019; Published 14 July 2019

Academic Editor: Giovanni Martinelli

Copyright © 2019 Pengfei Di et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract.

Methane (CH₄), the most abundant hydrocarbon gas in the atmosphere, plays an important role in global climate change. Quantifying the dissolved methane and its air-sea flux from hydrocarbon seeps is therefore of great importance. Large quantities of natural gas are emitted from the seafloor to the coastal ocean near the Lingtou Promontory, South China Sea. We quantified concentrations of methane in surface and bottom waters at 48 stations in a 56 km² study area. High spatial variability in dissolved methane concentrations was observed in the surface mixed layer (0.5 m water depth) and bottom water (water-sediment interface), with values ranging from 2.90 nmol L⁻¹ to 13570.02 nmol L⁻¹ and from 4.98 nmol L⁻¹ to 31740.02 nmol L⁻¹, respectively. The significant difference between concentrations of dissolved methane in surface and bottom waters suggests that most of the methane emitted from the seafloor is dissolved in the water column. The dissolution of methane in seawater may result in local oxygen depletion that may lead to ecological effects. The δ¹³C values of dissolved methane ranging from −59.76‰ to −48.59‰ indicate a mixture of biogenic and thermogenic gas sources. The average air-sea methane flux of Yinggehai Basin was 672.57 μmol m⁻² d⁻¹, which cannot be ignored in environment assessment. Coastal regions, especially with hydrocarbon seeps in shallow waters of the continental margin, may therefore be an important source of methane to the atmosphere.

1. Introduction

After water vapor and CO₂, methane (CH₄) is the most important greenhouse gas in the atmosphere and plays an important role in global climate change. Methane is produced in oceanic sediments either by methanogens or through the breakdown of organic molecules [1, 2]. Modern-day atmospheric methane concentrations of 1.77 ppmv (parts per million by volume) are more than twice the preindustrial value of 0.71 ppm [3, 4]. Compared with carbon dioxide, methane is a more potent greenhouse gas, having a global warming potential that is 23 times higher on a 100 yr timescale [3, 4]. It is estimated that methane is released into the atmosphere worldwide at a rate of about 503–610 Tg yr⁻¹ [5]. Although hydrocarbon seeps release about 8–65 Tg yr⁻¹ of methane into the ocean [6], only 4–15 Tg yr⁻¹ of methane is released into the atmosphere, accounting for about 1%–2% of the global atmospheric methane flux [7–12]. These values reveal that methane undergoes a complicated set of processes (involving both anaerobic and aerobic oxidation) in the ocean, with more than 85% of methane being consumed before reaching to the sea surface [13–16]. However, there is still substantial uncertainty surrounding estimates of the size and nature of methane sources and sinks and how their variations can affect atmospheric methane concentrations.

Natural hydrocarbon seeps in marine environments are widely distributed on the seabed of almost all continental margins, which are important sources of methane and other greenhouse gases to the ocean and the atmosphere [9, 17–19]. Quantifying methane discharge from hydrocarbon seeps and its flux to the atmosphere is a major unsolved issue regarding the marine methane cycle. Hydrocarbon seeps may release methane dissolved in pore waters or, in the case of oversaturation, in the form of gas bubbles into the ocean [9, 17, 18, 20, 21]. When methane is emitted as gas bubbles, a fraction of the methane in the bubbles dissolves in the seawater via gas exchange during the bubbles’ transport to the seawater surface, and the methane flux depends on release depth, bubble diameter, and the buoyancy force of the plume [22–24]. Methane can be released directly into the atmosphere from rising gas bubbles mainly in shallow waters (<100 m) while methane bubbles emitted from deep waters tend to become fully dissolved in the water column before reaching to the ocean surface. It has been shown that the flux and vertical transport of this methane are controlled by physical processes such as vertical mixing, turbulent diffusion, and upwelling [24, 25]. Bubble dissolution leads to patches of higher methane concentrations in the water column (from tens of nmol L⁻¹ up to several μmol L⁻¹), for example, in the Coal Oil Point seep field [19]. However, the dissolved methane flux arising from the dissolution of gas bubbles during transit through the water column or from the discharge of methane-rich pore fluids from the sediment into the water column is particularly difficult to quantify. The quantification of this indirect flux is critical for understanding the marine hydrocarbon contribution to the total atmospheric methane source.

Coastal regions are important sources of methane (13 Tg CH₄ yr⁻¹) to the atmosphere [5, 26, 27]. Hundreds of hydrocarbon seeps are discovered in the coastal regions of Yinggehai Basin [28–30]. However, the distribution of dissolved methane and its air-sea fluxes has not been quantified. Sources and sinks of the seeping methane remain unclear. Here, we determined the distribution of dissolved methane from seawater samples and estimated the methane air-sea flux in the Lingtou Promontory seep area.

2. Study Area

The Yinggehai Basin, located to the southwest of Hainan Island (16°50–20°00N, 107°00–111°50E), is one of the world’s largest hydrocarbon seep regions [28, 31–33]. The basin is characterized by abundant hydrocarbon seeps, pockmarks, and mud volcanoes on the seabed [28, 31–33]. More than 120 hydrocarbon seeps have been found on the seabed at water depths of <50 m along the eastern edge of the basin near the western coast of Hainan Island. At these seeps, the gas rises to the sea surface to form a nearshore bubble zone [28]. The total gas flux emitted from these hydrocarbon seeps to the water surface has been estimated as 294–956 m³ yr⁻¹ based on the displacement of water estimated using an inverted funnel [28], whereas a total methane flux of to has been estimated for these seeps based on extrapolation of data obtained over 420 h using a gas flux measuring device on one hydrocarbon seep [29, 30, 34].

The Lingtou Promontory seep field is one of the most active areas in the Yinggehai Basin for natural hydrocarbon seepage [29, 30]. Over 20 perennial hydrocarbon seeps are emitting gases within an area measuring approximately located ~300 m offshore Lingtou Promontory in Hainan Province, at water depths of 3–20 m (Figure 1(a)). It has been observed that gas bubbles (each up to 1–2 cm in diameter) are being emitted continuously from the hydrocarbon seeps on the seafloor (Figures 1(b) and 1(c)) and that these bubbles rise to the sea surface at about 10 cm s⁻¹ and release their gases into the atmosphere [29, 30, 35]. Methane is released at rates ranging from to from 20 hydrocarbon seeps in the Lingtou Promontory seep area, assuming that the hydrocarbon seeps have a similar gas flux [29, 30]. However, this region has not been surveyed for dissolved methane distributions and air-sea fluxes to date.

(a)

(b)

(c)

Figure 1: (a) Bathymetric map of the hydrocarbon seep area near Lingtou Promontory. The red dots show the distribution of the nearshore hydrocarbon seeps, and the black dots are the seawater sample grid. (b) Photograph of rising irregular gas bubbles from a seep site. (c) Gas bubbles at the sea surface.

3. Methods

On 19–20 August 2015, 96 seawater samples were sampled at 48 stations to quantify the dissolved methane concentration distribution along 4 west-east (W-E) transects from nearshore to the Yinggehai Basin (Figure 1(a) and Table 1). Sampling was carried out with a 5 L Niskin bottle coupled to a conductivity-temperature-depth (CTD) probe (RBR XR420) and a dissolved oxygen sensor (RBR) for the online monitoring of salinity, temperature, pressure, and dissolved oxygen (DO) concentrations in surface waters (0.5 m depth sampling level) and at the sea-sediment interface (bottom-water samples). The CTD sensors were calibrated to a temperature range of 2–35°C with a resolution of 0.002°C, to a salinity range of 0–70 mS cm⁻¹ with a resolution of 0.001 mS cm⁻¹, and to a depth range of 0–6000 m with a resolution of 0.001 m. The dissolved O₂ sensor could detect within the range 0–500 μM (saturation 0–120%) with a resolution of <1 μM (saturation 0.4%) [36].

Table 1: The CH₄ concentrations of bottom and surface seawater, as well as the O₂ concentration, temperature, water depth, salinity of all the sites, and the values in seawater and bubbles from the Lingtou Promontory seep area.

Station
Latitude
Longitude
Water depth (m)
CH₄ concentration (nmol L⁻¹)
δ¹³C (‰)
O₂ concentration (mL)
Salinity (‰)
Temperature (°C)

Dot 1
18°4152
108°4113
0.50
3.18
—
7.81
32.72
29.67

4.10
10.00
—
8.13
32.62
29.38

Dot 2
18°4137
108°4029
0.50
11.27
—
7.57
33.14
29.37

5.31
5472.08
—
7.82
33.21
29.16

Dot 3
18°4158
108°3930
0.50
7.19
—
7.42
33.41
29.21

6.48
9.93
—
7.91
33.38
29.13

Dot 4
18°4158
108°3857
0.50
12.09
—
7.49
33.48
28.92

7.10
11.06
—
7.94
33.37
29.00

Dot 5
18°4202
108°3828
0.50
19.74
—
7.31
33.49
29.12

7.50
23.80
—
7.38
33.33
29.09

Dot 6
18°4201
108°3751
0.50
36.10
—
7.59
33.43
28.82

8.07
10.95
—
7.49
33.26
28.61

Dot 7
18°4202
108°3701
0.50
19.55
—
7.43
33.39
28.84

7.30
4.98
—
7.63
33.35
28.71

Dot 8
18°4157
108°3558
0.50
64.70
—
7.48
33.36
28.74

5.34
28.54
—
7.82
33.24
28.74

Dot 9
18°4158
108°3500
0.50
9.65
—
7.39
33.39
28.71

6.30
26.31
—
7.64
33.32
28.68

Dot 10
18°4201
108°3400
0.50
68.95
—
6.94
33.36
28.86

7.67
9.13
—
7.23
33.36
28.78

Dot 11
18°4227
108°3402
0.50
7.62
—
7.01
33.37
28.96

6.41
79.85
—
7.47
33.36
28.81

Dot 12
18°4227
108°3501
0.50
1500.49
—
7.29
33.39
28.90

6.55
17.73
—
7.27
33.27
28.88

Dot 13
18°4232
108°3600
0.50
975.45
—
6.85
33.47
29.21

5.22
50.36
—
7.19
33.39
29.05

Dot 14
18°4243
108°3831
0.50
11.43
—
7.02
33.41
29.42

5.94
7.35
—
7.23
33.32
29.31

Dot 15
18°4228
108°3835
0.50
12.45
—
6.93
33.4
29.27

7.36
45.40
—
7.15
33.38
29.23

Dot 16
18°4225
108°3902
0.50
10.56

7.17
33.38
29.28

6.11
11.54

7.41
33.33
29.21

Dot 17
18°4224
108°3934
0.50
6.80
—
6.96
33.36
29.32

7.38
65.62
—
7.13
33.38
29.28

Dot 18
18°4233
108°3959
0.50
26.09
—
7.04
33.35
29.47

6.79
22.54
—
7.26
33.31
29.45

Dot 19
18°4230
108°4031
0.50
4140.60
—
7.12
33.23
29.68

6.42
17.98
—
7.38
32.98
29.66

Dot 20
18°4235
108°4105
0.50
16.67
—
7.18
33.17
30.04

5.48
9.01
—
7.67
33.15
30.02

Dot 21
18°4159
108°4104
0.50
19.15
—
7.22
33.17
29.98

4.94
9.42
—
7.85
33.22
29.93

Dot 22
18°4159
108°4129
0.50
14.95
—
7.58
32.96
30.32

4.7
390.64
—
8.08
32.93
30.31

Dot 23
18°4059
108°4059
0.50
12318.50
−59.17
7.15
33.04
29.55

3.44
2313.53
—
7.23
33.08
29.49

Dot 24
18°4159.5
108°4029
0.50
45.89
—
7.2
33.34
29.29

4.45
31740.02
−59.54
7.36
33.34
29.28

Dot 25
18°4059
108°4003
0.50
13577.35
−59.76
7.26
33.34
29.23

4.45
—
—
7.39
33.33
29.22

Dot 26
18°4056
108°3915
0.5
33.25
—
7.16
33.37
29.19

3.72
209.05
—
7.12
33.38
29.16

Dot 27
18°4059
108°3859
0.5
171.06
—
7.18
33.39
29.22

5.55
10.04
—
7.2
33.23
29.17

Dot 28
18°4059.9
108°3829
0.5
12.23
—
7.12
33.38
29.31

6.08
435.28
—
7.22
33.34
29.23

Dot 29
18°4059.5
108°3759
0.5
8.84
—
7.17
33.38
29.22

7.01
8.69
—
7.26
33.29
29.12

Dot 30
18°4059.3
108°3658
0.5
107.98
—
7.2
33.39
28.68

7.03
22.35
—
7.19
33.33
28.65

Dot 31
18°4059.7
108°3558.2
0.5
6.17
—
7.15
33.39
28.71

5.74
23386.77
−48.59
7.2
33.25
28.66

Dot 32
18°4101
108°3459.4
0.50
2.90
—
7.09
33.37
29.03

5.75
9.99
—
7.25
33.27
28.87

Dot 33
18°4059.7
108°3358
0.50
22.08
—
7.08
33.34
28.93

6.96
5.17
—
7.2
33.32
28.75

Dot 34
18°4131.6
108°3400
0.50
9.80
—
7.04
33.35
29.05

10.38
171.94
—
7.29
33.12
28.79

Dot 35
18°4129.4
108°3501
0.50
115.34
—
7.14
33.36
29.07

9.76
107.83
—
7.3
33.32
29.04

Dot 36
18°4128.6
108°3602
0.50
7.82
—
7.08
33.39
28.86

6.52
101.58
—
7.23
33.28
28.85

Dot 37
18°4128.9
108°3701
0.50
8.51
—
7.18
33.45
28.94

5.27
547.26
—
7.22
33.3
28.81

Dot 38
18°4129.8
108°3801
0.50
4.01
—
7.07
33.47
29.53

6.70
573.54
—
7.17
33.35
29.14

Dot 39
18°4129.9
108°3838.6
0.5
7.69
—
7.04
33.43
29.57

8.21
4.98
—
7.24
33.34
29.15

Dot 40
18°4129.8
108°3901
0.5
250.93
—
7.14
33.65
29.49

8.06
162.68
—
7.29
33.59
29.19

Dot 41
18°4129.3
108°3930.7
0.5
24.02
—
7.01
33.66
29.49

7.59
9.10
—
7.18
33.64
29.18

Dot 42
18°4129
108°4001
0.5
7.75
—
7.24
33.35
29.56

6.99
65.26
—
7.35
33.37
29.41

Dot 43
18°4128.4
108°4031.1
0.5
4.13
—
7.33
33.44
29.75

6.37
233.55
—
7.42
33.34
29.65

Dot 44
18°4158.4
108°3959.7
0.5
28.80
—
7.1
33.8
29.59

5.81
21.07
—
7.38
33.72
29.53

Dot 45
18°4131.2
108°4111.8
0.5
153.62
—
7.46
33.16
30.09

6.15
122.29
—
7.93
33.14
29.98

Dot 46
18°4054.6
108°4104
0.5
551.39
—
7.72
33.15
30.2

5.23
495.30
—
8.12
33.12
30.12

Dot 47
18°4058.7
108°4129.2
0.5
7.73
—
7.9
32.86
30.42

5.35
169.94
—
8.02
32.76
30.25

Dot 48
18°4132.4
108°4135.4
0.5
19.05
—
7.89
32.79
30.49

3.45
187.42
—
8.32
32.61
30.41

Dot 49
18°420.2
108°4128.1
0.5
14.00
—
8.05
32.82
30.49

3.6
11.92
—
8.59
32.7
30.3

YG
18°4115.7
108°4137.0
5.00
—
−35.98
—
—
—

Ys-1
18°41.136
108°41.304
0.50
—
−35.51
—
—
—

Data are taken from Huang et al. [28] and Di et al. [35].

All water samples, once collected, were stored in 122 mL crimp-top sample bottles. All sample bottles were flushed with two volumes of water and filled completely to eliminate bubbles. Two to three drops of saturated HgCl₂ were added to the samples after collection, and the bottles were immediately capped with butyl rubber stoppers and crimp-sealed. To prevent the headspace gas from escaping through the rubber stopper, all bottles were stored stopper-side down until analysis. All samples were transported to the laboratory, and a 10 mL N₂ headspace was introduced into each bottle as described by Valentine et al. [37]. Two aliquots of the headspace were each analyzed for methane using a Wasson/HP complete gas composition analyzer at the Guangzhou Institute of Geochemistry, Chinese Academy of Science (CAS), Guangzhou, China. Replicate analyses of samples yielded a precision of ±2% for samples with methane content. The methane concentration dissolved in seawater was calculated as described in Johnson et al. [38]:

where is the concentration of the gas to be measured in the liquid phase before equilibrium, is the concentration of the gas to be measured in the gas phase after equilibrium, is the Bunsen solubility of the gas to be measured (L L⁻¹ atm.⁻¹), is the gas constant (L atm. mol⁻¹ K⁻¹), and 22.356 is the molecular volume of methane (L mol⁻¹).

Seawater samples with high dissolved methane concentrations were analyzed to determine the stable carbon isotope composition of methane. Stable carbon isotope analyses were conducted using an isotope ratio mass spectrometer at the Guangzhou Institute of Geochemistry, CAS, Guangzhou, China. All isotopic ratios are presented in the δ notation with respect to the Vienna Pee Dee Belemnite (VPDB) standard and have an analytical error of <1‰.

The air-sea methane flux () was calculated as described in Leifer and MacDonald [39]:

where is the transfer velocity for methane at in situ temperatures (cm hr⁻¹), is the measured dissolved methane concentration in seawater (nM), and is the air-equilibrated seawater methane concentration (nM), which was calculated for in situ temperatures and salinities using the Bunsen solubility data of Wiesenburg and Guinasso [40]. We have assumed, for these calculations, an atmospheric methane mixing ratio of 1.80 ppmv, which in turn assumes an annual increase of ~7 ppbv [3]. The resulting flux is given in units of μmol m⁻² d⁻¹. The determination of the transfer velocity, , has been thoroughly discussed in Wanninkhof et al. [41]. For our purposes, we used the following relationship, as suggested by Wanninkhof [42], for wind speeds of <15 m s⁻¹:

where is the average wind speed at 10 m above the water surface at the time of measurement and was determined from Wanninkhof [42] using

where is the in situ temperature (°C). Values for constants (2102.2), (−131.54), (4.4931), (−0.08676), and (0.00070663) were taken from Wanninkhof [42].

Average wind speed data were measured using a revolving vane anemometer (GM8901, range: 0.3–45 m s⁻¹) at 0.5 m above sea level on-board and corrected to a standard height of 10 m by applying the following power law:

where is the mean wind speed at a height of , is the mean wind speed at 10 m, and is the effective height of the anemometer above the mean sea level. The air-sea flux was calculated for all the surface water samples. Owing to the potential inaccuracy of wind speed measurements and the parameterizations of the gas transfer velocity, there may be uncertainties surrounding the air-sea flux data.

4. Results and Discussion

4.1. Concentrations of Dissolved Methane

Methane concentrations for the 96 seawater samples collected at the Lingtou Promontory seep area are all above ~2 nmol L⁻¹ of the atmospheric equilibrium concentration (Table 1) [43]. The methane concentrations of surface seawater samples range from 2.90 nmol L⁻¹ to an anomalously high value of 13577.35 nmol L⁻¹ close to the hydrocarbon seep sites (Figure 2(a)). The average concentration for the surface seawater samples is 704.40 nmol L⁻¹, which is much higher than the maximal value in surface waters (~1800 nmol L⁻¹) measured in the Santa Barbara Channel (Coal Oil Point), one of the most active known hydrocarbon seep areas in the world [39]. The methane concentrations of the bottom-water samples range from 4.98 nmol L⁻¹ to 31740.02 nmol L⁻¹ with an average value of 1376.75 nmol L−0.1. The dissolved methane concentration data for the bottom-water samples reveal a distinct gas plume situated at the seafloor (Figure 2(b)). The anomalously high concentrations of methane dissolved in bottom waters are higher than the surface methane concentrations but much lower than the maximum methane concentration (2500 μmol L⁻¹) measured by the methane sensor at the hydrocarbon seep sites [29] as well as the calculated saturated methane concentration (1413 μM L⁻¹) for conditions of 29°C, 0.538 mol kg⁻¹ salinity, and 1.26 bar pressure [44]. Similar results have been reported in other gas seepage areas, such as the North Sea, south of the Dogger Bank, and Tommeliten, the central North Sea [45]. The difference value of the dissolved methane concentrations between surface waters and bottom waters may be attributed to removal by microbial methane oxidation and lateral dispersion by physical transport, favored by strong tidal currents and ocean current [43, 45–47].

Figure 2: The distribution of dissolved methane concentrations in bottom waters and surface waters, respectively. The plot was generated using the Ocean Data View Version 4.5.7 (https://odv.awi.de) gridding weighted averages.

Exceptionally high methane concentrations usually point to hydrocarbon seepage. Measurements of methane concentration can be used to detect a gas plume situated near the seafloor, and the transect profiles can reveal discrete maxima that indicate whether the methane released from gas bubbles was emitted from the hydrocarbon seeps or from a horizon where methane from different sources converge. We divided our data into four transects from north to south along the shore. Along the fourth transect, two stations with extremely high methane concentrations were found to be associated with locations of intense hydrocarbon seepage at water depths of 3–20 m (Figure 3). One station with high methane concentrations is close to the shore of the Lingtou Promontory at the surface, which indicates that methane was released from a horizon where different sources of methane converge. The other station with high methane concentrations is far offshore and in bottom waters, which indicates that methane was released from gas bubbles emitted from the hydrocarbon seeps. The high methane concentrations in bottom waters along the second and third transects, which eventually decrease offshore (Figure 3), indicate that methane is released from seafloor seeps. Surface methane concentrations were mostly in equilibrium with atmospheric concentrations along the second and third transects. Dissolved methane concentrations along the north transect were lower than in the other three transects, and surface methane concentrations were mostly in equilibrium with the atmosphere except for two locations (Figure 3), indicating that methane was being transported from nearby seafloor emissions by ocean currents. A similar result has been observed at 20 m water depth in the Coal Oil Point seep field near Santa Barbara, California [39].

Figure 3: East-west transects of dissolved methane concentrations at the Lingtou Promontory seep area. The red stars are the starting point.

4.2. Controls on Methane Distribution

Owing to the shallow depths (<20 m) and strong tidal currents, thermal or haline stratification does not occur in the Lingtou Promontory seep area because there are no salinity and temperature gradients between the surface and bottom waters (Figure 4). Due to the strong tidal currents and ocean currents, the dissolved O₂ concentrations remain in approximate equilibrium with atmospheric concentrations, with no gradients between the surface and bottom waters (Figure 4). In addition, the dissolved methane concentrations are not correlated with dissolved O₂ concentration, salinity, and temperature (Figure 4). Although dissolved methane concentrations in bottom waters were statistically higher than that in surface waters, the difference (on average ~48.8%) was much larger than that in the nearshore shallow coast area of the North Sea (on average ~14%) [43], because gas bubbles are transported a long distance by ocean currents when they have risen to the sea surface. Hence, on account of the shallow depths and well-mixed water column, there is a loss of methane between the bottom and surface waters, unlike in deeper and stratified areas such as Tommeliten and south of the Dogger Bank [43].

(a)

(b)

(c)

(d)

(e)

(f)

Figure 4: Dissolved methane concentrations in relation to dissolved oxygen concentration (a), salinity (b), and temperature (c) and comparison of temperature, salinity, and dissolved O₂ concentration in surface and bottom water (d–f).

The observed bubble emissions are responsible for generating the gas plume in the Lingtou Promontory (Figure 1). The methane maxima above the seafloor observed in the vertical profiles indicate a gaseous methane input from the seabed. Furthermore, the fact that methane maxima were observed above the seafloor suggests gas deposition from bubble dissolution. When gas bubbles rise through the water column, they expand because of the decrease in hydrostatic pressure and at the same time decrease in volume because of dissolution [48]. Owing to the dominating effect of the decrease in bubble size, the net buoyancy force decreases during ascent, and methane is deposited at water depths where hydrostatic equilibrium is reached and bubbles cannot continue moving. However, on account of the shallow water depths, the gas bubbles () contain approximately 95% methane on reaching the sea surface [24]. Therefore, there is little loss of methane from gas bubbles as they ascend from the bottom to the surface.

4.3. Air-Sea Methane Flux

Air-sea methane emission fluxes were estimated for water sampled at 0.5 m water depth in the surface mixed layer. The estimated fluxes range between 1.4 and 13058.44 μmol m⁻² d⁻¹ in the nearshore Lingtou Promontory (Figure 5). The median value is 672.57 μmol m⁻² d⁻¹, which is approximately four times the reported rate of methane emission in Santa Barbara Channel (Coal Oil Point; 180 μmol m⁻² d⁻¹), one of the most active marine seep areas in the world [39]. The mean value is 18 times higher than the global average flux values for continental shelves (21.6 to 36.29 μmol m⁻² d⁻¹ [26]) and four orders of magnitude higher than values characteristic of the open ocean (0.2–0.5 μmol m⁻² d⁻¹) [49]. However, it has been estimated that to of methane is emitted from hydrocarbon seeps [29, 30]. The total air-sea flux of methane in the nearshore Lingtou Promontory seep area is negligible compared with the flux of the methane bubbles. By analogy with the Lingtou Promontory seep area, other coastal regions of the Yinggehai Basin, such as the Yinggehai rivulet mouth, Yazhou Bay, the Nanshan Promontory, and the Tianya Promontory (shallower than 50 m), may emit more than 672.57 μmol m⁻² d⁻¹ of methane to the atmosphere [28]. Therefore, the coastal regions of the Yinggehai Basin in the hydrocarbon seep areas are significant sources of methane to the atmosphere, and the air-sea methane fluxes were probably underestimates.

Figure 5: The air-sea flux of methane at the Lingtou Promontory seep area. The average wind speed in this area was 5.1 m s⁻¹.

4.4. Methane Source

Methane-rich fluids forming gas flares at the seafloor migrate along faults and/or stratigraphic boundaries. Orange et al. [50] and Forrest et al. [51] have shown that the linear arrangement of hydrocarbon seeps on the seabed is controlled by a neighboring fault. All gas bubble flares located along the shore of Hanna Island are in the vicinity of the No. 1 Fault [28, 35]. Generally, anomalously high methane concentrations in seawater are associated with hydrocarbon seeps, such as the COP seep area and the western Spitsbergen shelf, which are in turn related to adjacent faults [39, 52–55]. In the Lingtou Promontory seep area, we further suggest that the sandy sediments facilitate the migration of methane-rich fluid to the seafloor. Hence, we assume fluid migration along structural pathways, particularly the No. 1 Fault. In addition, according to the seismic profile of the central diapir zone in the Yinggehai Basin, methane-rich fluids may be expelled by mud diapirs and migrate along the dipping strata [56]. A similar phenomenon was also reported for the offshore Prins Karls Forland at ~250 m water depth [57].

To further constrain the sources of methane, we measured the stable carbon isotopic composition of dissolved methane in four water samples with high methane concentrations that had been collected from Lingtou Promontory seep area. The values of two of these samples were −59.76‰ and −48.59‰ (Table 1). The fact that values in a sea-surface and sea-sediment interface sample are similar suggests that aerobic microbial oxidation is negligible in shallow waters (<10 m).

The values of gas bubbles collected from seeps and from the sea surface in the study area are −35.98‰ and −35.51‰, respectively (Table 1) [28, 35]. These values are distinctly higher than those measured in seawater, which reflects the mixing of methane from gas bubbles with biogenic methane generated in sediments. Without background values from the bottom and the surface ocean, we could not fully establish the mixing fraction of the methane. Notably, we were able to smell sulfurous odors in sediments collected in the shallow waters of the Lingtou Promontory seep area. It is concluded that the methane originally discharged at the seafloor was oxidized before sampling. However, we do not discount the possibility that the methane could have been removed by migration or preferential microbial oxidation [58, 59].

5. Conclusions

We observed high spatial variability in dissolved methane concentrations in surface and bottom waters in the Lingtou Promontory seep area. Dissolved methane concentrations in surface waters and bottom waters range from 2.90 to 13577.35 nmol L⁻¹ and from 4.98 to 31740.02 nmol L⁻¹, respectively, indicating oversaturation at all stations. The persistent anomalously high methane concentrations in seawater indicate an efficient transfer of dissolved methane from the seafloor to the surface waters. Furthermore, δ¹³C values of the dissolved methane in the studied seawater range from −59.76‰ to −48.59‰, indicating a mixed thermogenic and biogenic methane from the sediment. The measured average methane flux (~672.57 μmol m⁻² s⁻¹) is much higher than values characteristic of continental shelves. It is suggested that the coastal regions of Yinggehai Basin may emit more than 672.57 μmol m⁻² d⁻¹ of methane to the atmosphere. Coastal regions, especially shallow hydrocarbon seep areas, on the continental margin may therefore be an important hot spot of methane emissions to the atmosphere.

Data Availability

The data used to support the findings of this study are available from the corresponding author upon request.

Conflicts of Interest

The authors declare that there are no conflicts of interest regarding the publication of this paper.

Acknowledgments

We thank Dr. Baojia Huang for providing the coordinates of the gas seeps. This study was partially supported by the National Key R&D Program of China (2017YFC0307704) and the National Natural Science Foundation of China (41676046 and 41730528).

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